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Latest Miocene to Quaternary Deformation in the Southern 10.1002/2015JB012135 Chaiwopu Basin, Northern Chinese Tian Shan Foreland

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Latest Miocene to Quaternary Deformation in the Southern 10.1002/2015JB012135 Chaiwopu Basin, Northern Chinese Tian Shan Foreland PUBLICATIONS Journal of Geophysical Research: Solid Earth RESEARCH ARTICLE Latest Miocene to Quaternary deformation in the southern 10.1002/2015JB012135 Chaiwopu Basin, northern Chinese Tian Shan foreland Key Points: Honghua Lu1, Zhen Wang1, Tianqi Zhang1,2, Junxiang Zhao3, Xiangmin Zheng1, and Youli Li4 • Stratigraphic and subsurface data indicate existence of growth strata 1School of Geographic Sciences, East China Normal University, Shanghai, China, 2Now at Institute of Earth and • New magnetostratigraphy constrains 3 the inception of growth strata at Environmental Science, University of Potsdam, Potsdam, Germany, Institute of Crustal Dynamics, China Earthquake 4 ~6.4 Ma Administration, Beijing, China, Key Laboratory of Earth Surface Processes of Ministry of Education, Peking University, • Quaternary deformation is revealed Beijing, China by geomorphologic data Abstract Basinward propagation of fold and thrust belts is a crucial geological process accommodating Cenozoic crustal shortening within the India-Eurasia collision zone. Anticlinal growth strata in the southern Correspondence to: H. Lu, Chaiwopu Basin (a piggyback basin) of the northern Chinese Tian Shan foreland record basinward [email protected] encroachment of the Tian Shan along the Junggar Frontal Thrust Fault. A new magnetostratigraphic section constrains the onset of syntectonic growth strata at circa 6.4 Ma and suggests synchronous basinward Citation: thrusting and propagation of the Tian Shan. The intense alluviation in the southern Chaiwopu Basin ceased at Lu, H., Z. Wang, T. Zhang, J. Zhao, circa 0.55 Ma due to significant anticlinal growth and its resultant river incision. More recent anticlinal growth X. Zheng, and Y. Li (2015), Latest and deformation during the late Quaternary are revealed by folded river terraces developing across the Miocene to Quaternary deformation in H the southern Chaiwopu Basin, northern anticline. The terrace height profile indicates that terrace T1 has been vertically offset about 0.6 m by thrust Chinese Tian Shan foreland, J. Geophys. faulting since its formation at about 7 Ka. The stratigraphic and geomorphic data presented in this work are – Res. Solid Earth, 120, 8656 8671, helpful to understand the initiation of thrust-related folding, as well as aggradation and subsequent incision, doi:10.1002/2015JB012135. in foreland basins of the Tian Shan in relation to the India-Asia collision. Received 20 APR 2015 Accepted 13 NOV 2015 Accepted article online 17 NOV 2015 1. Introduction Published online 12 DEC 2015 Since the early Cenozoic, the India-Asia collision has driven deformation exerting a dominant control on the tectonic and topographic patterns of central Asia, including western China [Najman et al., 2001; Zhang, 2004] (Figure 1a). As a result of the collision, the Tian Shan (Shan means “mountains” in Chinese) has been tectoni- cally reactivated and intensely uplifted as crustal shortening propagated into its foreland basins [Windley et al., 1990; Avouac et al., 1993; Yin et al., 1998; Deng et al., 2000]. The well-exposed rocks in and adjacent to the arid to semiarid Tian Shan provide an ideal natural laboratory where the temporal and spatial history of tectonic deformation caused by the India-Asia convergence can be unraveled with exceptional clarity. Previous studies of the timing and magnitude of the Cenozoic tectonic deformation of the Tian Shan have utilized low-temperature thermochronology [e.g., Hendrix et al., 1994; Bullen et al., 2003; Sobel et al., 2006a, 2006b; Lu et al., 2013a; Yu et al., 2014], magnetostratigraphy [e.g., Chen et al., 2002, 2007; Charreau et al., 2005, 2006; Heermance et al., 2007, 2008; Sun et al., 2009; Lu et al., 2010a; Thompson et al., 2015], geological and geodetic investigations [e.g., Reigber et al., 2001; Zubovich et al., 2010], or geomorphologic data [e.g., Avouac et al., 1993; Burchfiel et al., 1999; Fu et al., 2003; Scharer et al., 2006; Lu et al., 2010b; Yang et al., 2012; Li et al., 2013]. Nonetheless, the detailed character, sequence, and magnitude of the structural, depositional, and geomorphic responses to the ongoing collision contain many gaps. Here we provide new stratigraphic and geomorphic data on the initiation of thrust-related folding, as well as aggradation and subsequent incision within a piggyback basin (i.e., the Chaiwopu Basin) of the northern Chinese Tian Shan foreland. The Chaiwopu Basin is situated in the easternmost part of the northern Chinese Tian Shan foreland (Figures 1a and 1b). Geomorphologically and tectonically, the basin lies in the transitional zone of the eastern Tian Shan (Bogda Shan and Balikun Shan) and the western Tian Shan: a diffuse N-S boundary which generally lies near the city of Urumqi (Figures 1a and 1b). Given its position at this transition, the Chaiwopu Basin is thus a key area to understanding the late Cenozoic deformation of the Tian Shan. At the southern margin of the basin, the small-scale Saerqiaoke anticline dominates the local topography [Lu et al., 2014] (Figures 1b and 1c). This anticline is causally linked with basinward thrusting along the north branch of southern Chaiwopu ©2015. American Geophysical Union. Fault (NSCF), which branches from the Junggar Frontal Thrust Fault (JFTF) bounding the northern Tian All Rights Reserved. Shan and its foreland basin [Liu et al., 2007]. However, the history of anticlinal growth and deformation LU ET AL. NORTHERN TIAN SHAN FORELAND DEFORMATION 8656 Journal of Geophysical Research: Solid Earth 10.1002/2015JB012135 Figure 1. (a) Map shows tectonic setting and topographical pattern of the Indian-Eurasian convergence zone. (b) Digital elevation model of the northern Chinese Tian Shan foreland where fold and thrust belts I to III characterize the regional topography. (c) Geological map in the southern Chaiwopu Basin where thick Quaternary alluviums deposited as alluvial fans F1 and F2 of the Urumqi River. Circles with numbers show the sampling sites for optically stimulated luminescence (OSL) dating, as reported in Table 1. LU ET AL. NORTHERN TIAN SHAN FORELAND DEFORMATION 8657 Journal of Geophysical Research: Solid Earth 10.1002/2015JB012135 remains unclear, with little stratigraphic and geomorphic evidences to precisely date the late Cenozoic tectonic activity in the southern Chaiwopu Basin. In foreland basins, detailed sedimentological and geomorphological investigations are helpful to understand the tectonic evolution of the basin [e.g., Molnar et al., 1994; Burbank et al., 1996; Burchfiel et al., 1999; Burbank and Anderson, 2011; Yang and Li, 2011; Yang et al., 2014; Thompson et al., 2015]. The main aim of this work is to develop a chronology of the late Cenozoic deformation in the southern Chaiwopu Basin of the northern Chinese Tian Shan foreland by integrating stratigraphic and geomorphic data. Our results help to reveal the activity of major faults in the basin and further to understand their seismic behavior: a focus that is significant given the active deformation and high seismicity in the modern Tian Shan and its foreland basins [Deng et al., 2000; Reigber et al., 2001]. 2. Geological Background As one of the largest and most active orogenic belts in the Asia inland, the EW-trending Tian Shan has experi- enced a complex geological history. Previous studies [e.g., Windley et al., 1990; Yin et al., 1998; Deng et al., 2000] have revealed that the ancestral Tian Shan arose from several block collisions during the Late Devonian-Early Carboniferous and Late Carboniferous-Early Permian, along with the formation of a suite of EW-trending strike-slip and thrust faults (Figure 1a). The Mesozoic deformation of the range was dominated by relative tectonic stability during the Triassic-Late Jurassic, followed by active deformation during the Late Jurassic-Early Cretaceous [Lu et al., 2010a]. The subsequent relative stability during the latest Mesozoic- Paleogene caused the beveling of topography within the Tian Shan [Allen et al., 1991; Bullen et al., 2003]. As a result of the Cenozoic India-Asia collision, the Tian Shan range has been tectonically reactivated and gradually encroached into its foreland basins [Deng et al., 2000; Lu et al., 2010a, 2013a]. In the northern Chinese Tian Shan foreland, such a geological process has formed three fold and thrust belts known as belts I to III that characterize the regional topography (Figure 1b). Situated in the easternmost part of the northern Chinese Tian Shan foreland, the Chaiwopu Basin is separated from the Junggar Basin to the northwest by the Xi Shan (i.e., the easternmost part of fold and thrust belt I) (Figure 1b), a low mountain range with elevations of 1–2 km. The basement rocks of the Chaiwopu Basin com- prise Permian to Triassic strata [Gao, 2004]. The basin fill consists of Tertiary and Quaternary strata. The Tertiary comprises the Donggou Group (Cretaceous-Eocene) and the Manas (Oligocene), Qianshan (Miocene), and Changjihe (Pliocene) Formations, and the lithology is dominated by lacustrine mudstone, sandstone, and con- glomerate. In general, the basement rocks and Tertiary strata are exposed on both the southern and northern margins of the Chaiwopu Basin due to tilting, thrusting, and folding. The overlying Quaternary strata are massive alluvial conglomerates. Where the Urumqi River flows into the lowland southern Chaiwopu Basin, two episodes of Quaternary alluvial fan deposition (the fans F1 and F2)areapparent[Lu et al., 2014] (Figure 1c). Stratigraphically, the fan F1 conglomerates (designated as Saerqiaoke Gravel by Zhou et al.
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